Geology of the Northern Convoy Range, Victoria Land, Antarctica

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Geology of the northern Convoy Range, Victoria Land, Antarctica

Giovanni Capponi , Chiara Montomoli , Stefano Casale & Matteo Simonetti

To cite this article: Giovanni Capponi , Chiara Montomoli , Stefano Casale & Matteo Simonetti (2020) Geology of the northern Convoy Range, Victoria Land, Antarctica, Journal of Maps, 16:2, 702-709, DOI: 10.1080/17445647.2020.1822218 To link to this article: https://doi.org/10.1080/17445647.2020.1822218

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Full Terms & Conditions of access and use can be found at https://www.tandfonline.com/action/journalInformation?journalCode=tjom20 JOURNAL OF MAPS 2020, VOL. 16, NO. 2, 702–709 https://doi.org/10.1080/17445647.2020.1822218

Science Geology of the northern Convoy Range, Victoria Land, Antarctica Giovanni Capponi a, Chiara Montomoli b, Stefano Casalec and Matteo Simonettib aDISTAV, University of Genoa, Genoa, Italy; bDipartimento di Scienze della Terra, University of Turin, Turin, Italy; cDipartimento di Scienze della Terra, University of Pisa, Pisa, Italy

ABSTRACT ARTICLE HISTORY In this paper, we supply a geological map of the area between 76°–76°30′S and 159°–163°E, that Received 14 November 2019 was the only missing portion to complete an entire coverage of Victoria Land, ﬁlling the gap Revised 17 March 2020 between the GIGAMAP program (to the north) and the maps by the New Zealand Antarctic Accepted 7 September 2020 program (to the south). The mapped area encompasses an early Paleozoic basement, and a ﬂ KEYWORDS at-lying cover of sedimentary and igneous rocks, Permo-Triassic to Jurassic in age. The Geological mapping; Convoy basement consists of large bodies of the Granite Harbour Igneous Complex, a granitic Range; Victoria Land; complex linked to the Ross Orogeny. After the early Paleozoic Ross Orogeny, the area was Antarctica uplifted and eroded, and the sandstones of the Beacon Supergroup were deposited on the resulting erosion surface. The Beacon Supergroup sandstones were in turn covered and in most cases incorporated into the volcanic and sub-volcanic rocks of the Jurassic Ferrar Group.

1. Introduction Field activity was organized in daily missions from the Italian Mario Zucchelli Station (2017/2018) and In northern Victoria Land (Antarctica), the activity of in a period of stay in a tent camp (2018/2019), at German and Italian geologists has resulted in several Starr Nunatak (75°54′S162°35′E), in order to be able geological maps (Carmignani et al., 1987; Ganovex & to reach the most distant sectors of the study area. Map- ItaliAntartide, 1991; Ganovex & ItaliAntartide, 2003; ping was coupled with the collection of rock samples Ganovex Team, 1987). Additionally, in 1995, German that we studied in thin section after the expeditions, and Italian geologists signed an agreement of in order to better characterize the lithotypes. cooperation (the GIGAMAP program, Capponi The topographic base comes from a mosaic of two et al., 2002) to cover the entire northern Victoria 1:250,000 USGS quadrangles i.e. the Convoy Range Land region with new geological mapping at the and the Franklin Island quadrangles; they were used scale 1:250,000. In the Dry Valleys area, geological both in the field and for the final construction of the mapping has been carried out principally by New Main Map. The Franklin Island quadrangle includes Zealand geologists (Cox et al., 2012; Gunn & Warren, a large area of the Ross sea, with two small islands in 1962; Pocknall et al., 1994), and their maps, together the eastern part, i.e. the Beaufort and Franklin islands, with the GIGAMAP maps, give an almost complete that we were not able to visit and map. Because of this, coverage of Victoria Land. However, the area between ′ we excluded from the Franklin Island quadrangle the 76° and 76°30 S (the northern part of the Convoy area covering the sea and the unvisited islands and Range and Franklin Island quadrangles, 1:250,000 join the trimmed area with the Convoy Range topographic sheets by USGS) has yet to be mapped quadrangle. in any detail and is devoid of updated geological observations: the aim of this paper is to supply the geological map of this area. 3. Geological framework The Convoy Range-Franklin Island quadrangles encompass an early Paleozoic granitic basement, and 2. Methods a flat-lying cover of sedimentary and igneous rocks, The 1:250,000 scale Main Map covers an area of about spanning in age from Permo-Triassic to Jurassic. 6665 km2. Mapping was performed during two Ita- The early Paleozoic basement consists of large liAntartide expeditions (XXXIII Expedition in austral bodies of the late Cambrian-early Ordovician Granite summer 2017/2018 and XXXIV Expedition in austral Harbour Igneous Complex, enclosing minor bodies of summer 2018/2019). Field work was carried out by a metamorphic rocks of the Wilson Terrane. The three-person team and was helicopter-supported. Wilson Terrane includes low-medium- to high-grade

CONTACT Giovanni Capponi [email protected] DISTAV, University of Genoa, Corso Europa 32, 16132 Genoa, Italy © 2020 The Author(s). Published by Informa UK Limited, trading as Taylor & Francis Group This is an Open Access article distributed under the terms of the Creative Commons Attribution License (http://creativecommons.org/licenses/by/4.0/), which permits unrest- ricted use, distribution, and reproduction in any medium, provided the original work is properly cited. JOURNAL OF MAPS 703 metamorphic rocks of inferred Precambrian-Cambrian coast of the Ross Sea, and are characterized by the age, deformed and metamorphosed in the early Paleozoic association of the syn-tectonic Larsen granodiorite Ross Orogeny (late Cambrian–early Ordovician). After with post-tectonic granite. Such rocks represent a typi- the Ross Orogeny, the area was uplifted and eroded, cal arc-related calc-alkaline orogenic suite, linked to and the sandstones of the Beacon Supergroup were the subduction zone magmatism associated to Ross deposited on the resulting peneplain surface. The Beacon Orogeny. The dominant rock type is an unfoliated to sandstones were in turn intruded by the sills of the Jurassic weakly foliated metaluminous biotite granite and Ferrar Dolerite, and in most cases incorporated into the granodiorite. Radiometric age data (U–Pb on zircon) dolerite. indicate that the emplacement sequence of the Granite Harbour Igneous Complex spanned nearly 30 Myr, from 521 to 481 Ma (Bomparola et al., 2007; Giaco- 4. Wilson Terrane mini et al., 2007); no data specifically related to this 4.1. Wilson metamorphic complex (Wa) quadrangle are available. At many places, the dominant granitoid type is In this area, the Wilson Metamorphic Complex intruded by the younger Irizar Granite (GHgra), that includes low-to medium-grade metasediments; such is a homogeneous, unfoliated, equigranular, medium- rocks are restricted to small bodies and slivers, occur- to coarse-grained syeno-monzogranite, characterized ring at Mt Murray, south of Mt Chetwynd and at by pink–red colour, due to the presence of pink alkali northern Walker Rocks. The protoliths of these meta- feldspar. A 489 ± 4.4 Ma U–Pb zircon crystallization sediments appear to belong to a unique sequence of age was obtained at Cape Irizar (Rocchi et al., 2009), fi ne- to medium-grained siliciclastic sediments, with in agreement with Di Vincenzo et al. (2003),whosup- intercalations of conglomerate (Walker Rocks, Figure plied an age of 486.1 ± 8.4 Ma by Ar–Ar and Rb–Sr 1(A)). Their depositional age is widely unknown and a techniques. Major Irizar outcrops are in the northern late Neoproterozoic to Cambrian age is likely, on the cliffs of Mt Gauss and in the western slopes of Mt Ende- basis of detrital white mica geochronology (Di Vin- vour; Irizar granite occurs also as m-thick dykes, with cenzo et al., 2014; Tessensohn & Henjes-Kunst, the same age of emplacement (Rocchi et al., 2009). 2005). Such metasediments underwent metamorphic equilibration from low to high grades, during the 4.3.2. Diorite and gabbro (GHt) Ross Orogeny (Carmignani et al., 1987; Casnedi & Large bodies of unfoliated to weakly foliated micro- Pertusati, 1989; Castelli et al., 1997; Lombardo et al., gabbro-microdiorite occur in the area of Mt Smith, 1987; Skinner, 1989). beneath the light grey granite. Due to the dark colour, they resemble Ferrar dolerite, but the clear gradational 4.2. Johnnie Walker formation (Wf) contact with respect to the overlying granites (Figure 1 (B)) rules out this option and supports a genetic This formation crops out at the southern area of relation with the Granite Harbour Igneous Complex. Walker Rocks, in the centre of the study area, and con- Other rocks related to the Granite Harbour Igneous sists of unmetamorphosed andesite, brecciated ande- Complex are the Vegetation Lamprophyres, that con- site, rhyolite and granophyric rhyolite (Tessensohn stitute a widespread association of hypabyssal tabular et al., 1990). The rock types and the field observations intrusions (Rocchi et al., 2009), with hundreds of sub- suggest a formation in a sub-volcanic environment. vertical mafic dikes, with thicknesses around 1 m, and Such rocks unconformably overlie the meta- an overall strike between NE–SW and NNE–SSW. morphic rocks of the Wilson Terrane and are intruded Dykes sampled at Bruce Point, Cape Hickey and Mt by the Granite Harbour Intrusives. The age of these Endevour returned an Ar–Ar age around 490 Ma rocks is unknown, but must be older than the empla- (see Rocchi et al., 2009, for details). cement of the ∼490 Ma Granite Harbour Igneous Complex. The temporal position of these rocks, between Ross-age metamorphic rocks and the post- 5. Beacon supergroup (Bs) tectonic Granite Harbour Igneous Complex, is quite The base of the Beacon Supergroup is represented by a unusual and requires a rapid and short-lived uplift remarkable erosion surface which is equivalent to the event, between metamorphism and ∼490 post-tec- Kukri Peneplain as defined in the Dry Valleys (Barrett tonic granite intrusion (Tessensohn et al., 1990). et al., 1986). In this quadrangle, however, the outcrops of Beacon sandstone are quite limited and only at Mt Smith do small bodies of sandstone that rest above the 4.3. Granite harbour igneous complex erosion surface, between the granitic basement and the 4.3.1. Granodiorite and granite (GHgr–GHgra) overlying dolerite (Figure 1(C)). In a cliff south of Mt The Granite Harbour Igneous Complex rocks are Chetwynd, a layer of Beacon sandstone, that is con- restricted to the western part of the area, close to the tinuous for about 1 km, lies below the Ferrar dolerite, 704 G. CAPPONI ET AL.

Figure 1. (A) Deformed conglomerate cropping out at the Walker Rocks, showing flattened clasts; (B) gradational contact between the Granite Harbour Granite (GHgr) and the Granite Harbour microgabbro-microdiorite (GHt) in the Mt Smith area. A Ferrar Doler- ite dike (Fd) crosscutting the granite is present (red, detail in Figure 3(B)); (C) Beacon Sandstone body above the Kukri erosion surface, between the granitic basement (GHgr) and the overlying dolerite (Fd) in the Mt Smith area; (D) beds of Beacon sandstone rich in organic matter, truncated by Ferrar Dolerite. McLea Nunatak. but the erosion surface is not visible; the Granite Har- occur at the nameless nunatak SE of Beckett Nunatak, bour granitoids are not exposed here. at McLea Nunatak and at Reckling Peak, with the pres- Elsewhere the Beacon outcrops are restricted to ence of petrified trunk and coal measures (Figure 1 100–1000 m-large bodies, encapsulated in the Ferrar (D)); however, no age-related fossils were found so far. dolerite, that locally truncates the stratification of the Layers with clay galls (chip or flake of clay sandstone (Figure 1(D)). embedded in a sandy matrix) occur as well, and in Due to the scarcity and limited extension of out- places, beds display syn-sedimentary deformation crops, it was impossible to differentiate the Beacon and slumping. In most places, the stratification is hori- rocks in their Permian and Triassic-Jurassic sequences zontal or shallowly inclined; only in a few cases, beds (i.e. the Takrouna and Section Peak formations, of Beacon sandstone are steeper or even vertical (e.g. respectively) and so they remain undifferentiated. at Reckling Peak), but this is clearly linked to the Cross bedding is common; ripple marks (western emplacement of the Ferrar rocks (Figure 2). slopes of Mt Endevour) and trace fossils (Mt Smith) are present in places. Beds rich in organic matter 6. Ferrar volcanic suite 6.1. Ferrar dolerite (Fd) The Ferrar Dolerite represents the dominant rock unit in the area (Elliot et al., 1997) and constitutes the majority of the Beckett Nunatak, of the Mt Armytage, of the Shultz Peak, of the Trinity and Jarina Nunatak; it also occurs at the top of the Kirkwood Range and at Mt Smith. Such rocks consist of tholeiitic dolerite sills and minor dykes, which form spectacular cliffs commonly characterized by a typical columnar jointing (Figure 3(A)). AK–Ar age of 174 ± 10 Ma has been reported for these rocks from the Mount Murchison quadrangle Figure 2. Bodies of Beacon sandstone (Bs) suspended in the (Brotzu et al., 1989). Fleming et al. (1997) indicate an Ferrar Dolerite (Fd) at the Reckling Peak. Ar–Ar age of 176.7 ± 8 Ma for the Ferrar tholeiitic JOURNAL OF MAPS 705

Figure 3. (A) columnar jointing of the Ferrar Dolerite in the Mt Smith area; (B) Ferrar Dolerite dike (Fd) with sharp margins crosscutting the Granite Harbour Granite (GHgr) in the Mt Smith area; (C) Outcrop appearance of the Mawson Formation at the Reckling Peak; clasts and rafts of Beacon sediment (Bs) are present. rocks as a whole. Encarnación et al. (1996) provided outcrops at Battlements Nunatak and at Reckling more precise zircon and baddeleyite U–Pb ages for the Peak, both in the western part of the quadrangle. Ferrar dolerite, of 183.6 ± 1.0 Ma. This age is slightly The relationships with the overlying Kirkpatrick older than the other ages quoted before but within error. Basalt are preserved at Battlements Nunatak. At Mt Smith the dolerites are emplaced over the This formation is made of volcaniclastic rocks and Kukri erosion surface, with the occasional interposi- the most abundant lithologies are debris avalanche tion of small bodies of Beacon sandstone. Minor deposits, unsorted to poorly sorted lapilli tuff and dykes are also present in the underlying granitic base- breccia, often with clasts and rafts of Beacon sediment ment (Figure 3(B)). (Figure 3(C)). Sandstone and siltstone with associated South of Mt Chetwynd, the dolerite occurs above a basaltic lavas also occur. Cementation by quartz and level of Beacon sandstone, that is continuous for about zeolites is very common. 1 km, but the erosion surface is not exposed here. In the eastern cliffs of Mt Endevour the Ferrar sills occur on the erosion surface with no interposition of 6.3. Kirkpatrick basalt (Kb) any Beacon sandstone. At Mt Murray, the dolerite In this quadrangle, the basalt flows of the Kirkpatrick occurs above the Wilson Terrane rocks, with no Bea- Basalt are limited to small outcrops in the eastern part con sandstone in between. Elsewhere the base of the of the Battlement Nunatak and a very small outcrops Ferrar sills is not exposed. at McLea Nunatak. Locally they are associated with volcaniclastic sandstone (e.g. at Battlement Nunatak). K–Ar dates from the Mesa Range basalts (Mt 6.2. Mawson formation (Mf) Murchison quadrangle) indicate a 178 Ma minimum The Mawson Formation (Ballance & Watters, 1971; age for the whole lava sequence (Elliot & Foland, Borns & Hall, 1969) is the equivalent to the Exposure 1986). A 40Ar/39Ar age of 174.2 ± 1 Ma was obtained Hill Formation (Elliot et al., 1986) and is limited to the by Mcintosh et al. (1986). 706 G. CAPPONI ET AL.

7. Quaternary deposits rocks. In the Mt Murray area, a mineral lineation (L ), steeply plunging toward the E, is present. The Quaternary deposit mapping was conducted on 1 Another result is the weak foliation that locally the basis of previous studies (Cox et al., 2012; Gunn affects the Granite Harbour granitoids. & Warren, 1962; Pocknall et al., 1994) and following On the base of the NE–SW strike of the subvertical criteria used for the existing Terra Victoria geomor- Irizar and Vegetation dykes, Rocchi et al. (2009) phological and geological cartography (Baroni et al., suggested a NW–SE extension during the latest stages 2004, Baroni, Biasini, Bondesan, et al., 2005; Baroni, of the Ross Orogeny. Biasini, Cimbelli, et al., 2005; Baroni, Frezzotti, et al., 2005; Capponi et al., 2002; Salvatore et al., 1997). Glacial deposits consist in ridges (moraines) and/or 8.2. Post-ross tectonics scattered boulders (glacial drift) resting on bedrock or The most striking feature related to the post-Ross tec- regolith. For instance, both features can be simul- tonics is represented by the regional unconformity taneously appreciated at Beckett Nunatak, where along the pre-Beacon erosion surface. This surface is different erratic boulder lines can be interpreted as the equivalent to the Kukri Peneplain as defined in different moraines, left by ice masses as they fluctuated the Dry Valleys (Barrett et al., 1986) and testifies to over time. At the same site, a poorly organized glacial the uplift and erosion of the Ross Orogen. This erosion drift leans directly on the lower outcropping bedrock. surface is visible at Mt Smith, Mt Gauss, Mt Murray, The above-described configuration can also be Mt Chetwynd and at the eastern slopes of Mt Ende- observed at other sites of the study area, e.g. The Mit- vour; at all sites, it appears to be horizontal or very ten, Mt Murray and Mt Armytage. Several floating close to the horizontal. moraines occur in the study area, and one of the long- The elevation of the erosion surface is not constant est moraine of this type is located at Reckling Peak and is around 1200 m at Mt Endevour, 1100 at Mt (Figure 4); it is several hundred meters long and is Chetwynd and Mt Gauss, around 1000 m at Mt Mur- mainly comprised by angular and sub-angular blocks, ray and around 1300 m at Mt Smith. So the Mt Gauss– with a smaller portion of thin sediment. Mt Murray sector appears to be lowered with respect Slope deposits are mainly located along the flanks to the sectors to the south (Mt Endevour) and to the of the topographic relief (e.g. Mt Murray and Beckett north (Mt Smith). Such changes in the height of the Nunatak) and consist of clasts and blocks with differ- erosion surface can be due to original changes in ent sizes, and angular to sub-angular shapes. reliefs along the surface, related to differential erosion of the Cambrian-Ordovician basement complex in the area. An alternative possibility is the post-Kukri 8. Tectonics activity of faults with some vertical offset, though, 8.1. Ross tectonics due to the ice coverage, the occurrence of such faults is not evident in the field. ff The e ects of the Ross deformation are limited to the Beacon strata (S0) are generally sub-horizontal or development of the tectonic foliation (S1) that can be dip toward the W–SW with very low angle (see observed in the rare slivers of Wilson Terrane schist. Main Map, stereonet A); no evidence of regional Both at Mt Murray and at the eastern slopes of Mt deformation is present. Variations in the angle of Endevour, such tectonic foliation is steeply dipping dip are just a local feature (e.g. at Reckling Peak), to the NE (see Main Map, stereonet A), in this way due to the local deformation caused by the emplace- matching the regional strike of most Wilson Terrane ment of the Ferrar rocks. Minor faults, affecting the Granite Harbour Igneous Complex, have been observed at Mt Chetwynd, in the northern part of the Kirkwood Range, and at the Walker Rocks, in the central sector of the study area. In the Mt Chetwynd area, faults (Sf) strike mostly E– W and dip at moderate angles, both toward the N and the S (see Main Map,stereonetB),suggestingthe occurrence of two conjugated fault sets (Sf1 and Sf2). Striae (Lf) along N-dipping faults plunge toward the NW at a moderate angle (see Main Map, stereonet C). No striae were observed on S-dipping faults. At the Walker Rocks, two fault sets have been – recognized: one set (Sf1) strikes NE SW and the – other one (Sf2) strikes NW SE (see Main Map, stereo- Figure 4. The floating moraine at the Reckling Peak. net B). Faults belonging to the first set are subvertical JOURNAL OF MAPS 707

Figure 5. (A) thin levels of dark material associated to fault planes crosscutting the Irizar Granite at the Walker Rocks; (B) cata- clasite in the Granite Harbour granitoid, Shoulder Mountain. or steeply dipping toward the SE or NW; faults of the Complex. As they are very similar to the Ferrar second set dip at a moderate angle toward the NE. Dolerites at the outcrop scale, we suggest that Striae (Lf) along fault surfaces generally plunge at the occurrence of gradational contacts with the low angles toward the NE and only locally steeply granites, where present, can be a key feature to plunge toward the SSE (see Main Map, stereonet C). distinguish these rock units. Taking into account the orientation of the striae on – The occurrence of sedimentary rocks of the Beacon fault planes in the two areas, it is likely that at least Supergroup is very limited in this area and it is not some of them accommodate a component of strike- possible to specifically assign them to stratigraphic slip movement. In particular, in the Mt Chetwynd intervals found within the Devonian to Triassic- area, two faults show striae with a pitch of 50° and Jurassic portions of the section. 31°, whereas at the Walker Rocks two faults show – Several fault systems in the Mt Chetwynd and striae with a pitch of 8° and 15°. This can be related Walker Rocks areas are associated to dark seams to the relevance of strike-slip faulting in the post- of very fine material with the presence of injection Ross evolution of northern Victoria Land (Salvini veinlets testifying the presence of ultracataclasite et al., 1997; Storti et al., 2001). All the other faults and/or possible pseudotachylites. Further petro- have down-dip striae with pitch near to 90°. graphic investigations could discriminate the On one fault in the Chetwynd area and on both sets presence of such structures. of faults in the Walker Rocks, we observed dark seams – Difference in elevation of the erosion surface can be of very fine material, 1–10 mm thick, parallel to the due to original relief along such surface, linked to fault planes (Figure 5(A)). In some cases, we observed differential denudation of the Ross orogenic belt, injection veinlets, 2–3 mm in length. Even if the occur- or alternatively to the post-Kukri activity of dip- rence of injection veinlets is typical of pseudotachy- slip faults, though not evident in the field. lites, we cannot exclude that these structures could be related to the presence of ultracataclasites or to later mineralization. At the Shoulder Mountain Software (southern Kirkwood Range) cataclasites and protoca- taclasites of centimetric thickness crosscut the Granite Topographic Base was assembled with the software fi Harbour granitoid (Figure 5(B)). Qgis 2.18 and map nal layout was made with Adobe Illustrator CC 2018.

9. Discussion and conclusion Acknowledgements Detailed geological mapping, structural and petrogra- Thanks are due to Piero Pertusati for providing his provi- phical analyses allow us to compile a new geological sional geological map and to Gianluca Cornamusini for map which completes the coverage of Victoria Land his help with the Beacon stratigraphy. Skilful helicopter and highlights some key features of this area: piloting by Bob McElhinney, Dave Sowman and Justin Gloag made this work possible. Help by Gianluca Ippolito, ﬁ – Stefano Piantoni and Danilo Collino both in the eld and rocks of the Wilson Metamorphic Complex in this at the Starr Nunatak camp is greatly acknowledged. Careful area are restricted to small bodies and slivers sur- revisions by Brendan Dyck, Mike Shand and Timothy Paul- rounded by the granitoid of the Granite Harbour sen helped to improve the manuscript. Igneous Complex. – We recognized and mapped large bodies of unfoliated to weakly foliated microgabbro-microdior- Disclosure statement ite, belonging to the Granite Harbour Igneous No potential conﬂict of interest was reported by the author(s). 708 G. CAPPONI ET AL.

Funding Ferrar Group (Jurassic) in the Beardmore Glacier area (Antarctica). In M. D. Turner & J. F. Spettstoesser fi fi This work bene ted from the logistical and nancial support (Eds.), Geology of the central transantarctic mountains. of the Italian Programma Nazionale di Ricerche in Antar- Antarctic research Series (vol. 36, pp. 339–428). tide [grant number PNRA16_00042, responsible American Geophysical Union G. Capponi]. Bomparola, R. M., Ghezzo, C., Belousova, E., Griffin, W. L., &O’Reilly, S. Y. (2007). Resetting of the U–Pb zircon sys- tem in Cambro-Ordovician intrusives of the deep freeze ORCID range, northern Victoria Land, Antarctica. Journal of Petrology, 48(2), 327–364. https://doi.org/10.1093/ Giovanni Capponi http://orcid.org/0000-0002-9237-3212 petrology/egl064 Chiara Montomoli http://orcid.org/0000-0002-0364-5395 Borns, H. W., & Hall, B. A. (1969). A reinvestigation of the Mawson Tillite, Victoria Land, Antarctica. Antarctic Journal of the United States, 4, 133–134. 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